1. Introduction
The Guatemala Suture Zone (GSZ) (Brueckner et al. Reference Brueckner, Avé lallemant, Sisson, Harlow, Hemming, Martens, Tsujimori and Sorensen2009; Flores et al. Reference Flores, Martens, Harlow, Brueckner and Pearson2013) is a composite east-west trending, left-lateral strike-slip zone that defines the current boundary between the North American and Caribbean plates in Guatemala (Fig. 1a). This zone has been active since at least the Miocene (Rogers & Mann, Reference Rogers and Mann2007; Authemayou et al. Reference Authemayou, Brocard, Teyssier, Simon-Labric, Guttiérrez, Chiquín and Morán2011; Obrist-Farner et al. Reference Obrist-Farner, Eckert, Locmelis, Crowley, Mota-Vidaure, Lodolo, Rosenfeld and Duarte2020), but its geological record reflects processes of both accretionary and collisional orogenesis dating back to the Cretaceous and consistent with the development of the Circum-Caribbean suture system (Draper et al. Reference Draper, Gutiérrez and Lewis1996; Harlow et al. Reference Harlow, Hemming, Lallemant, Sisson and Sorensen2004; García-Casco et al. Reference García-Casco, Torres-Roldán, Iturralde-Vinent, Millán, Nuñez-Cambra, Lázaro and Rodríguez-Vega2006; Maresch et al. Reference Maresch, Kluge, Baumann, Pindell, Krückhans-Lueder and Stanek2009). Since the magnitude of lateral displacement between different crustal blocks within the GSZ during the Cenozoic is mostly unknown, the along-strike variation in the overall architecture of the Cretaceous orogen is thus far uncertain.
Figure 1. Geological setting of the Guatemala Suture Zone with inset of location within the Circum-Caribbean region. (a) Tectonic overview of the North American-Caribbean-Cocos triple junction region showing the location of the Guatemala Suture Zone (white rectangle) as well as major basement exposures of southern Mexico, Guatemala and Belize (modified after Kesler et al. Reference Kesler, Josey and Collins1970; Anderson et al. Reference Anderson, Burkart, Clemons, Bohnenberger and Blount1973; Ortega-Gutiérrez et al. Reference Ortega-Gutiérrez, Solari, Ortega-Obregón, Elías-Herrera, Martens, Morán-Icál, Chiquín, Keppie, De León and Schaaf2007, 2018; Ratschbacher et al. Reference Ratschbacher, Franz, Min, Bachmann, Martens, Stanek, Stübner, Nelson, Herrmann, Weber, López-Martínez, Jonckheere, Sperner, Tichomirowa, Mcwilliams, Gordon, Meschede and Bock2009; Martens et al. Reference Martens, Weber and Valencia2010; Weber et al. Reference Weber, González-Guzmán, Manjarrez-Juárez, Cisneros De León, Martens, Solari, Hecht and Valencia2018). (b) Geological map of the Guatemala Suture Zone indicating the study area. Relevant basement units are labelled with black cursives, whereas major fault zones are indicated by bold lines and blue cursives. NMM: North Motagua mélange; SMM: South Motagua mélange.
The GSZ contains a complex mixture of continental margin rocks and remnants of oceanic lithosphere, some of which enclose eclogite, blueschist and other high-pressure (HP) metamorphic rocks spanning in age from Berriasian to Campanian (Harlow et al. Reference Harlow, Hemming, Lallemant, Sisson and Sorensen2004; Brueckner et al. Reference Brueckner, Avé lallemant, Sisson, Harlow, Hemming, Martens, Tsujimori and Sorensen2009; Yui et al. Reference Yui, Maki, Usuki, Lan, Martens, Wu, Wu and Liou2010; Martens et al. Reference Martens, Brueckner, Mattinson, Liou and Wooden2012; Flores et al. Reference Flores, Martens, Harlow, Brueckner and Pearson2013; Maldonado et al. Reference Maldonado, Weber, Ortega-Gutiérrez and Solari2018a). Of special interest is the occurrence of gneiss-hosted eclogites in the Chuacús Complex (Ortega-Gutiérrez et al. Reference Ortega-Gutiérrez, Solari, Ortega-Obregón, Elías-Herrera, Martens, Morán-Icál, Chiquín, Keppie, De León and Schaaf2004), directly adjacent to the Motagua fault zone, which provide evidence that the GSZ includes a portion of deeply subducted continental crust. Recent research has focused on investigating the timing, conditions and context of this process in the area (Martens et al. Reference Martens, Brueckner, Mattinson, Liou and Wooden2012; Martens et al. Reference Martens, Tsujimori and Liou2017; Maldonado et al. Reference Maldonado, Ortega-Gutiérrez and Hernández-Uribe2016, Reference Maldonado, Weber, Ortega-Gutiérrez and Solari2018a, Reference Maldonado, Ortega-Gutiérrez and Ortíz-Joya2018b). At the same time, the question arises as to what the origin of the subducted crust is and what relationships it has with other pre-Cretaceous terranes of the Circum-Caribbean region. Most of these terranes cover an area throughout Mexico, Central America and northern South America and are commonly referred to as ‘peri-Gondwanan’ terranes (e.g. Oaxaquia, Maya block, Chortí block and Mérida Andes). In particular, the kinship between the Chuacús Complex and the composite continental Maya (North America) and Chortí (Caribbean) blocks (Dengo, Reference Dengo1969; Donnelly et al. Reference Donnelly, Home, Finch, López-Ramos, Dengo and Case1991) remains mostly speculative. Based on apparent lithostratigraphic similarities and the tectonic arrangement of the GSZ resembling a Cretaceous Himalaya-style orogen (O’Brien, Reference O’Brien2019), some authors have suggested that the Chuacús Complex originally formed part of the Maya block (Ratschbacher et al. Reference Ratschbacher, Franz, Min, Bachmann, Martens, Stanek, Stübner, Nelson, Herrmann, Weber, López-Martínez, Jonckheere, Sperner, Tichomirowa, Mcwilliams, Gordon, Meschede and Bock2009; Martens et al. Reference Martens, Tsujimori and Liou2017; Maldonado et al. Reference Maldonado, Weber, Ortega-Gutiérrez and Solari2018a). Accordingly, the current paradigm is that the Maya’s margin was subjected to southward subduction during the Cretaceous, a model that requires a plate configuration similar to that of prevailing palinspastic reconstructions (e.g. Pindell et al. Reference Pindell, Maresch, Martens and Stanek2012). However, interpretations about the origin and evolution of the Chuacús Complex have changed considerably over the last two decades. Research is moving towards a more comprehensive understanding of its protracted evolution as well as palaeogeographic connections and significance.
Most previous works combine either petrologic or structural analysis with geochronological data (Ortega-Gutiérrez et al. Reference Ortega-Gutiérrez, Solari, Ortega-Obregón, Elías-Herrera, Martens, Morán-Icál, Chiquín, Keppie, De León and Schaaf2004; Ratschbacher et al. Reference Ratschbacher, Franz, Min, Bachmann, Martens, Stanek, Stübner, Nelson, Herrmann, Weber, López-Martínez, Jonckheere, Sperner, Tichomirowa, Mcwilliams, Gordon, Meschede and Bock2009; Martens et al. Reference Martens, Brueckner, Mattinson, Liou and Wooden2012; Maldonado et al. Reference Maldonado, Weber, Ortega-Gutiérrez and Solari2018a, Reference Maldonado, Ortega-Gutiérrez and Ortíz-Joya2018b), and only a few studies integrate geochemical, isotopic and geochronological information (Solari et al. Reference Solari, Tuena, Gutíerrez and Obregón2011; Maldonado et al. Reference Maldonado, Solari, Schaaf and Weber2023), essential to propose petrogenetic interpretations. This has resulted in a still sparse and incomplete database for the Chuacús Complex. In a couple of recent studies, we focused on both the petrogenesis of eclogite protoliths (Maldonado et al. Reference Maldonado, Solari, Schaaf and Weber2023) and the general characterization of the hosting granitoid gneisses (Maldonado et al. Reference Maldonado, Ortega-Gutiérrez and Ortíz-Joya2018b). In this contribution, we integrate and complete the existing database, coupling new U-Pb and trace element zircon data with whole-rock Sm-Nd and Lu-Hf isotope analyses of metagranitoids and metapelites from the Chuacús Complex, in order to refine understanding of the petrogenesis, sedimentary record and nature of the tectonothermal events in this region and its role in the Rodinia and Pangea supercontinent cycles.
2. Geological setting
2.a. The Guatemala suture zone
The GSZ includes the Polochic, Baja Verapaz, Motagua and Jocotán fault zones (Fig. 1b) that currently define diffuse tectonic limits, bounding distinctive crystalline basement units with ages varying from the Mesoproterozoic to the Jurassic (Ortega-Gutiérrez et al. Reference Ortega-Gutiérrez, Solari, Ortega-Obregón, Elías-Herrera, Martens, Morán-Icál, Chiquín, Keppie, De León and Schaaf2007). The updated pre-Cretaceous lithostratigraphy of this area was recently summarized in Maldonado et al. (Reference Maldonado, Solari, Schaaf and Weber2023), so only a brief overview is given below.
Between the Polochic and Baja Verapaz fault zones, Neoproterozoic or early Palaeozoic low-grade metasediments (San Gabriel Unit) and cross-cutting deformed Ordovician-Silurian granitoids (Rabinal Granite) compose the Rabinal Complex of Maya affinity (Ratschbacher et al. Reference Ratschbacher, Franz, Min, Bachmann, Martens, Stanek, Stübner, Nelson, Herrmann, Weber, López-Martínez, Jonckheere, Sperner, Tichomirowa, Mcwilliams, Gordon, Meschede and Bock2009; Ortega-Obregón et al. Reference Ortega-Obregón, Solari, Keppie, Ortega-Gutiérrez, Solé and Morán-Icál2008; Solari et al. Reference Solari, García-Casco, Martens, Lee and Ortega-Rivera2013; Solari et al. Reference Solari, Ortega-Gutiérrez, Elías-Herrera, Schaaf, Norman, De León, Ortega-Obregón, Chiquín and Ical2009). This sequence is unconformably overlain by continental sedimentary rocks of the Carboniferous Sacapulas Formation (Santa Rosa Group) (Ortega-Obregón et al. Reference Ortega-Obregón, Solari, Keppie, Ortega-Gutiérrez, Solé and Morán-Icál2008; Solari et al. Reference Solari, Ortega-Gutiérrez, Elías-Herrera, Schaaf, Norman, De León, Ortega-Obregón, Chiquín and Ical2009). Altogether, these units are overthrust in places by ultramafic slices of the Baja Verapaz ophiolitic unit, which represent remnants of the Caribbean oceanic crust, formed in the Jurassic-Cretaceous by mid-ocean ridge activity and intraoceanic subduction (Giunta et al. Reference Giunta, Beccaluva, Coltorti, Mortellaro, Siena and Cutrupia2002; Beccaluva, Reference Beccaluva1995). The southern limit of the Rabinal Complex corresponds to the Baja Verapaz fault zone, a south-southwest-dipping system with sinistral transpressive kinematics developed during the Late Cretaceous (Ortega-Obregón et al. Reference Ortega-Obregón, Solari, Keppie, Ortega-Gutiérrez, Solé and Morán-Icál2008), along which the Rabinal Complex is in thrust contact with the eclogite-bearing Chuacús Complex (Ortega-Gutiérrez et al. Reference Ortega-Gutiérrez, Solari, Ortega-Obregón, Elías-Herrera, Martens, Morán-Icál, Chiquín, Keppie, De León and Schaaf2004). Recent studies have shown that the Chuacús Complex recorded a protracted evolution since the Mesoproterozoic, including several pulses of magmatism (see Section 2.b below). This continental HP belt is bounded to the south by the left-lateral Motagua fault system, where it is tectonically overlain by serpentinite mélange wedges (North Motagua mélange) that are part of a typical collisional flower structure (Giunta et al. Reference Giunta, Beccaluva, Coltorti, Mortellaro, Siena and Cutrupia2002). The juxtaposition of the Chuacús Complex and the North Motagua mélange occurred before the latest Cretaceous (Martens et al. Reference Martens, Brueckner, Mattinson, Liou and Wooden2012); however, the original spatial relationships were later disrupted by recent fault activity. Serpentinite mélanges north and south of the Motagua fault zone include blocks of HP moderate- to low-temperature metamorphic rocks, recording a process of oceanic subduction throughout the Cretaceous (Harlow et al. Reference Harlow, Hemming, Lallemant, Sisson and Sorensen2004; Tsujimori et al. Reference Tsujimori, Sisson, Liou, Harlow and Sorensen2006; Brueckner et al. Reference Brueckner, Avé lallemant, Sisson, Harlow, Hemming, Martens, Tsujimori and Sorensen2009; Yui et al. Reference Yui, Maki, Usuki, Lan, Martens, Wu, Wu and Liou2010; Flores et al. Reference Flores, Martens, Harlow, Brueckner and Pearson2013). The Las Ovejas Complex and the San Diego Phyllite are the southernmost basement units of the GSZ, exposed from the Motagua to the Jocotán fault zone and traditionally assigned to the Chortí block (Donnelly et al. Reference Donnelly, Home, Finch, López-Ramos, Dengo and Case1991). These units are tectonically juxtaposed and record independent geological evolutions. The Las Ovejas Complex is an assemblage of Jurassic to Cretaceous metaigneous and metasedimentary rocks and Cenozoic plutons that experienced amphibolite-facies metamorphism in the late Eocene, whereas the San Diego Phyllite consists of post-Cambrian low-grade metasediments metamorphosed in the Triassic (Torres de León et al. Reference Torres De León, Solari, Ortega-Gutiérrez and Martens2012).
2.b. The Chuacús complex
The Chuacús Complex forms the internal basement massif of the GSZ, containing the region’s deepest piece of continental crust and the oldest rocks known so far in Guatemala (Maldonado et al. Reference Maldonado, Solari, Schaaf and Weber2023). It consists of an arcuate, ∼220 km long metamorphic belt that includes an eclogite-bearing continental sequence (hereafter referred to as the HP suite) exposed along the Palibatz–Rabinal transect of the Sierra de Chuacús (Fig. 2). The metamorphism of the HP suite reflects a process of continental subduction and collision spanning from middle to Late Cretaceous (Martens et al. Reference Martens, Brueckner, Mattinson, Liou and Wooden2012; Maldonado et al. Reference Maldonado, Weber, Ortega-Gutiérrez and Solari2018a). The limits of the HP suite are not well known, but eclogite relicts have not been reported in other sectors of the massif (e.g. Sierra de las Minas; Fig. 1b). Since the predominant structural trend in the Sierra de Chuacús is defined by a NW-SE-striking, SW-dipping axial-plane foliation, the across-strike extension of the HP suite might be controlled by NE-directed thrust stacking and erosion that left deeper levels exposed in this area (Fig. 2). Its along-strike continuation is interrupted to the northwest and southeast by the Baja Verapaz and Motagua fault zones.
Figure 2. Simplified geological map and interpretative section of the Chuacús high-pressure suite exposed in the Sierra de Chuacús (modified after Maldonado et al. Reference Maldonado, Ortega-Gutiérrez and Ortíz-Joya2018b, Reference Maldonado, Weber, Ortega-Gutiérrez and Solari2018a). Geometric symbols highlight sample locations, eclogite occurrences and type localities of relevant lithodemic units in the area. Sample labels, including previously studied eclogites, are shown together with their corresponding U-Pb zircon ages in million years. Ages marked with superscripts were obtained previously by 1: Maldonado et al. (Reference Maldonado, Weber, Ortega-Gutiérrez and Solari2018a) and 2: Maldonado et al. (Reference Maldonado, Solari, Schaaf and Weber2023). MDA: maximum depositional age; MiPA: minimum protolith age. BVFZ: Baja Verapaz fault zone; NMM: North Motagua mélange.
In general, the HP suite can be described in terms of a metaigneous group including granitoid gneiss, amphibolite and retrogressed eclogite and a metasedimentary group of interlayered mica schist and paragneiss, marble, quartzite and calc-silicate rocks (Fig. 2) (cf. Martens et al. Reference Martens, Tsujimori and Liou2017). However, recent improvements in the geological database allow to define some informal lithodemic units, most of which still lack a cartographic representation, and thus, only their type localities are shown (triangles) in Figure 2:
1) Palibatz schist : consists of a garnet mica schist widely exposed in the southern Sierra de Chuacús, typically occupying a structurally upper position within the HP suite (Fig. 2). This unit includes coarse-grained layers containing the diagnostic HP assemblage garnet + phengite + kyanite + rutile (Ortega-Gutiérrez et al. Reference Ortega-Gutiérrez, Solari, Ortega-Obregón, Elías-Herrera, Martens, Morán-Icál, Chiquín, Keppie, De León and Schaaf2004; Maldonado et al. Reference Maldonado, Ortega-Gutiérrez and Ortíz-Joya2018b). Maldonado et al. (Reference Maldonado, Ortega-Gutiérrez and Ortíz-Joya2018b) obtained a garnet/whole-rock Lu-Hf age of 96 ± 2 Ma, as well as ca. 74 Ma U-Pb ages from late-stage zircon and monazite. Detrital zircon U-Pb data indicate post-Cryogenian (< ca. 690 Ma) deposition of the sedimentary protolith of this unit, whereas its chemical features suggest hemipelagic sedimentation and provenance from mature continental crust (Solari et al. Reference Solari, Tuena, Gutíerrez and Obregón2011).
2) Pachajob gneiss : is a folded and locally migmatized granitic gneiss exposed about 3 km west of the Pachajob village. This unit is structurally below the Palibatz schist and contains a HP paragenesis including Ca-rich garnet + phengite + rutile. U-Pb zircon dating determined the protolith crystallization age of the Pachajob gneiss at ca. 990 Ma (Maldonado et al. Reference Maldonado, Ortega-Gutiérrez and Ortíz-Joya2018b). This rock is high-silica and peraluminous in composition, and its trace element concentrations are consistent with a protolith formed by anatexis of a high-grade metamorphic crust (Maldonado et al. Reference Maldonado, Ortega-Gutiérrez and Ortíz-Joya2018b).
3) Cubulco unit : is composed of variably deformed metagranitoids and subordinated amphibolite with eclogite relicts. It is well-exposed southwest of Cubulco town, in the northern Sierra de Chuacús, occupying an intermediate structural position within the HP suite. The original intrusive relationships between mafic dikes and host metagranitoids, as well as relic magmatic textures overgrown by HP minerals, are visible in the less deformed portions. However, diagnostic HP mineral assemblages are not always recognizable in the Cubulco unit. Granitic protoliths formed at ca. 1100 Ma, and their relatively high abundances of high-field-strength elements (HFSE) suggest a precursor magma sourced from an enriched mantle (Maldonado et al. Reference Maldonado, Ortega-Gutiérrez and Ortíz-Joya2018b). Recently, Maldonado et al. (Reference Maldonado, Solari, Schaaf and Weber2023) have reported U-Pb zircon ages between 1098 ± 46 and 1026 ± 29 Ma for OIB-like eclogite protoliths from the Tres Cruces–Palibatz sector, suggesting that the Cubulco unit constitutes a bimodal magmatic suite, probably related to intraplate magmatism.
4) Agua Caliente unit : comprises a sequence of HP metagranitoids, retrogressed eclogites and amphibolites, well-exposed along the gorge of the Agua Caliente river, where it is structurally below the Palibatz schist and probably hosted by the Cubulco unit. This unit displays variable degrees of partial melting and deformation. Metagranitoids range from massive megacrystic bodies to flaser gneiss, with mineral assemblages including Ca-rich garnet + epidote + phengite + rutile. Eclogite occurs as enclaves or lenses aligned subparallel to the foliation planes and range from pristine to strongly amphibolitized or albitized. Protolith ages of metagranitoids and eclogitized metabasites from this unit range from ca. 230 to 210 Ma (Solari et al. Reference Solari, Tuena, Gutíerrez and Obregón2011; Martens et al. Reference Martens, Brueckner, Mattinson, Liou and Wooden2012; Maldonado et al. Reference Maldonado, Ortega-Gutiérrez and Ortíz-Joya2018b, Reference Maldonado, Solari, Schaaf and Weber2023), thus constituting a Late Triassic bimodal suite. U-Pb zircon data and geochemistry of the Agua Caliente unit suggest an origin related to variable participation of an enriched mantle/crustal source and a contribution of Mesoproterozoic continental material (Maldonado et al. Reference Maldonado, Solari, Schaaf and Weber2023). The HP suite also includes MORB-like eclogites with probable Jurassic (ca. 170–160 Ma) protoliths (Maldonado et al. Reference Maldonado, Solari, Schaaf and Weber2023) that are considered part of the Agua Caliente unit.
5) El Chol unit : consists of a polymetamorphic sequence of strongly retrogressed eclogite (amphibolite), omphacite-bearing gneiss, as well as metre-scale leucosome layers and deformed pegmatites, which lies structurally below the Agua Caliente and Cubulco units. This sequence is the structurally lowest level within the HP suite where eclogite relics are clearly preserved. The polymetamorphic character of the El Chol unit prevents a conclusive determination of protolith ages. Eclogite protoliths may have formed in two stages, at ca. 1310 and 1030 Ma (Maldonado et al. Reference Maldonado, Solari, Schaaf and Weber2023), but zircon from these rocks show complex U-Pb spectra, with main age populations at the Ediacaran (ca. 600 Ma), the late Silurian (ca. 420 Ma) and the Late Triassic (ca. 220 Ma). The youngest group is related to the widespread migmatization of this unit (Solari et al. Reference Solari, Tuena, Gutíerrez and Obregón2011; Maldonado et al. Reference Maldonado, Solari, Schaaf and Weber2023). Some eclogites from the El Chol unit show subduction geochemical signatures and could have formed in an extensional arc setting, whereas others have OIB-type compositions similar to the Cubulco eclogites.
3. Samples, methods and data handling
3.a. Samples
Seven granitoid gneiss samples from the Palibatz-Rabinal transect of the Sierra de Chuacús were used in this study. Five of them correspond to previously studied samples in Maldonado et al. (Reference Maldonado, Ortega-Gutiérrez and Ortíz-Joya2018b), and the other two (CH88 and CH89) were collected ca. 10 km northwest of Cubulco, along the trace of the Baja Verapaz fault zone (Fig. 2). The term ‘granitoid’ is used hereafter to refer to these variably deformed rocks (Maldonado et al. Reference Maldonado, Ortega-Gutiérrez and Ortíz-Joya2018b). Additionally, two metapelite samples (CH3 and CH9) from the Palibatz schist, and two others (CH24 and CH35) from a metapelite sequence exposed in the northern flank of the Sierra de Chuacús were studied. Sample CH3 was collected from an outcrop in the Tanilar River, ca. 2 km north of Palibatz. Sample CH9 is from the Saltán River near the Pachajob village and was previously studied by Maldonado et al. (Reference Maldonado, Weber, Ortega-Gutiérrez and Solari2018a). Samples CH24 and CH35 were obtained from outcrops along the El Chol-Rabinal road in the Pachirax creek and around El Apazote village; both samples were investigated earlier by Maldonado et al. (Reference Maldonado, Ortega-Gutiérrez and Hernández-Uribe2016). Sample information is summarized in Table 1.
Table 1. Studied samples from the Chuacús high-pressure suite
*WGS84 UTM coordinates (15N).
†Analytical data presented in this study: 1 = Sm-Nd and Lu-Hf whole-rock isotopes; 2 = zircon trace element data; 3 = zircon U-Pb data.
3.b. Zircon U-Pb isotope and chemical analysis
Zircon crystals were employed from all four metapelite samples and two granitoids (CH88 and CH89) for U-Pb isotope analysis using laser ablation inductively coupled plasma mass spectrometry (LA-ICP-MS). Trace element concentrations in zircon from all seven granitoid samples were also determined in situ by LA-ICP-MS. Standard errors associated with individual analyses are reported at 2s level. Analytical procedures and results are presented in the online Supplementary Material at http://journals.cambridge.org/geo.
U-Pb discordance is the log ratio distance to the maximum likelihood composition on the concordia line (Vermeesch, Reference Vermeesch2021). Adaptive kernel density estimates (Vermeesch, Reference Vermeesch2012) were used to evaluate the age spectra and to determine maximum depositional ages for each metasedimentary sample. For this purpose, a discordance filter based on the log ratio distance to the concordia composition, a discordance cut-off value of 10% and single-grain concordia ages were used, as suggested by Vermeesch (Reference Vermeesch2021).
3.c. Sm-Nd and Lu-Hf isotope analysis
All samples were used for whole-rock Sm-Nd and Lu-Hf isotope dilution analysis. Initial 143Nd/144Nd and 176Hf/177Hf isotope data for granitoid samples were recalculated at the crystallization ages, determined by U-Pb zircon dating (Maldonado et al. Reference Maldonado, Ortega-Gutiérrez and Ortíz-Joya2018b; this work). For metapelites from the Palibatz schist and northern Chuacús, an age of 500 Ma was assumed based on U-Pb zircon data obtained in this work. A description of sample processing and isotope analytical methods is presented in the online Supplementary Material at http://journals.cambridge.org/geo.
Depleted mantle (TDM) Sm-Nd model ages were calculated using present-day isotopic values of Liew and Hofmann (Reference Liew and Hofmann1988) and the decay constant (λ) value for 147Sm of Lugmair and Marti (Reference Lugmair and Marti1978). For Lu-Hf, TDM model ages were determined according to the present-day values of Vervoort et al. (Reference Vervoort, Patchett, Albarède, Blichert-Toft, Rudnick and Downes2000) and the λ176Lu value of Scherer et al. (Reference Scherer, Münker and Mezger2001) and Söderlund et al. (Reference Söderlund, Patchett, Vervoort and Isachsen2004). Epsilon (ε) Nd and εHf values were calculated using chondritic uniform reservoir (CHUR) values after Bouvier et al. (Reference Bouvier, Vervoort and Patchett2008).
4. Results
4.a. U-Pb zircon geochronology
4.a.1. Cubulco unit
Samples from the Cubulco unit correspond to concordant layers, tens of metres thick, within a mylonitic gneiss sequence affected by the Baja Verapaz fault zone. Sample CH88 is a leucocratic granitoid gneiss with plagioclase augen, quartz, white mica, K-feldspar (≤ 5%), biotite, epidote, titanite, carbonate, apatite and zircon. Zircon crystals occur as elongated prisms (up to 500 μm long) displaying concentric and oscillatory zoning in cathodoluminescence (CL) images (Fig. 3). Forty-seven analyses from this sample yield concordant to moderately discordant (≤ 22%) results. A group of 32 analyses with discordances below 5% show a spread along concordia by ca. 100 m.y. and provide a weighted mean 207Pb/206Pb age of 1026 ± 10 Ma (MSWD = 0.6) (Fig. 4a). One slightly discordant date at ca. 1100 Ma is interpreted as inherited.
Figure 3. Post-ablation cathodoluminescence images of representative zircon crystals from (a–b) the Cubulco unit, (c) the Palibatz schist and (d) the northern Chuacús metapelite. Laser spots (white open circles) are labelled with the corresponding 206Pb/238U ages in million years. Note that each zircon is shown at a different scale.
Figure 4. U-Pb zircon isotope data of granitoid gneisses from the Cubulco unit. (a–b) Wetherill concordia diagrams plotted with error ellipses at the 2σ level (MSWD = mean square of the weighted deviates for age homogeneity or isochron fit). Grey open ellipses were discarded for the upper intercept age calculation.
Sample CH89 is a mesocratic granitoid gneiss that consists of plagioclase, quartz, white mica, epidote, K-feldspar (≤ 10%) and Fe-Ti oxide, with minor amounts of titanite, garnet, calcite, zircon and apatite. Zircon occurs as slightly rounded equant grains (up to 400 μm in size) with subtle concentric zoning. Forty-five analyses from this sample are concordant to slightly discordant (≤ 15%) and reflect a small amount of Pb loss. Forty analyses with discordances below 5 % produce a weighted mean 207Pb/206Pb age of 1013 ± 7 Ma (MSWD = 0.7) (Fig. 4b).
4.a.2. Palibatz schist
Samples from the Palibatz schist are coarse-grained metapelites that contain quartz, phengite, garnet and kyanite, as well as accessory minerals including rutile, Fe-Ti oxide, monazite, zircon and apatite. Zircon grains are variable in size and morphology; most of them include detrital cores displaying concentric, oscillatory and planar zoning patterns with dark overgrowth rims (Fig. 3). One hundred and eighty-six analyses were collected on 181 zircon grains from sample CH3 (Palibatz), of which 5 grains were double-analysed for core-rim dates. Most zircons are highly discordant (>30%) and scattered, reflecting distinct discordia trends with lower intercept ages between 150 and 50 Ma (Fig. 5a). Only 15 analyses passed a discordance filtering of −2–10%, which show density peaks at ca. 1486, 1256, 926 and 66 Ma. Similar density peaks are obtained by using 207Pb/206Pb ages of the whole dataset (not shown). The apparent age of 926 Ma is taken as the maximum depositional age of the sedimentary protolith, whereas the youngest peak corresponds to metamorphic zircon overgrowths.
Figure 5. U-Pb zircon isotope data of metapelite samples from the Palibatz schist and northern Chuacús. (a–d) Wetherill concordia diagrams plotted with error ellipses at the 2σ level. Insets show single-grain discordia trends (blue lines) and kernel density estimates (KDEs) (Vermeesch, Reference Vermeesch2012) for data below a discordance cut-off value of 10%, where x-axis denotes single-grain concordia age in million years and y-axis shows the frequency of data. Discordance is defined as the log ratio distance to the maximum likelihood composition on the concordia line (Vermeesch, Reference Vermeesch2021).
In sample CH9 (Pachajob), most zircon analyses (51%) are concordant or slightly discordant (≤10%), spreading along concordia between ca. 1580 and 850 Ma (Fig. 5b). The remaining discordant data indicate different discordia trends, the majority with lower intercept ages below 100 Ma. Fifty-five ages within the 10% discordance cut-off produce density peaks at ca. 1532, 1435, 1190, 1134, 1000, 920 and 71 Ma. The two youngest peaks provide the maximum depositional age of the sedimentary protolith and the age of metamorphic zircon crystallization in sample CH9, respectively.
4.a.3. Northern Chuacús metapelite
Sample CH24 (Pachirax) is a pelitic schist that consists of garnet porphyroblasts in a matrix mainly composed of phengite, paragonite, quartz, chloritoid and rutile, with minor amounts of epidote, chlorite, Fe-Ti oxide, kyanite, apatite and zircon. Most zircon grains display relatively high-CL cores with concentric, oscillatory, planar and sector zoning patterns, rimmed by darker overgrowth domains (Fig. 3). One hundred and nineteen out of 182 grains analysed are acceptable in terms of concordance (≤10%), with the majority falling along the concordia between ca. 1740 and 830 Ma (Fig. 5c). Age density peaks occur at ca. 1484, 1280, 1150, 1000 and 847 Ma. Two younger grains are concordant at ca. 509 (Th/U = 0.542) and 416 (Th/U = 0.016) Ma, but the age of ca. 847 Ma offers the more robust constraint on the maximum deposition age of the sample. Discordant grains (≥ 10%) delineate a discordia trend towards an apparent Silurian-Devonian lower intercept.
Sample CH35 (El Apazote) is a pelitic schist that contains staurolite porphyroblasts in a matrix of phengite, quartz, paragonite, garnet, chlorite, kyanite and chloritoid, plus accessory phases like rutile, apatite and zircon. Zircon crystals are analogous to those from sample CH24. Sixty-one laser spots were performed targeting both cores and rims. Core analyses mostly yielded concordant results in the 1670–799 Ma range (Fig. 5d), and 40 grains are acceptable for interpretation. Major density peaks occur at ca. 1543, 1105 and 987 Ma, with the youngest population providing the maximum depositional age of the protolith. The remaining analyses were collected on zircon rims and yielded discordant results (11–51% disc.), corresponding to different discordia trends with lower intercept ages towards the late Mesoproterozoic, early Palaeozoic and Triassic.
4.b. Zircon trace element compositions
A total of 338 points measurements were performed on zircons from all seven granitoid samples, comprising the Cubulco granitoids of ca. 1100 Ma (CH73, CH74) and 1030–1010 Ma age (CH88, CH89), the Pachajob gneiss of ca. 990 Ma age (CH10) and the Agua Caliente granitoids of ca. 225 Ma age (CH20, CH55).
Trace elements span a wide range of concentrations, both within individual samples and between them, including relevant elements in zircon like U (16–3920 μg/g), Th (3–1830 μg/g), Hf (6590–20500 μg/g) and Ti (0–78 μg/g) (Fig. 6). Most of the analysed zircons have Th/U values between 0.1 and 0.5; however, zircon from the Agua Caliente granitoids are characterized by relative high Th/U values around 1, whereas zircons from the granitoid CH89 (Cubulco unit) are typically below 0.1 (Fig. 6a). Titanium contents are highest in zircon from the Cubulco and Pachajob granitoids (up to 78 μg/g in CH74) and lowest in those from the Agua Caliente unit (up to 12 μg/g) (Fig. 6b). As a whole, the analyses show a rough positive correlation between Ti and Hf. The application of the Ti-in-zircon thermometer of Ferry and Watson (Reference Ferry and Watson2007), assuming a value of αTiO2 (0.6) in the range of silicic magmas (Hayden & Watson, Reference Hayden and Watson2007), indicates average crystallization temperatures of 848 ± 56 °C (n = 179, 1SD), 848 ± 27 °C (n = 103, 1SD) and 741 ± 60 °C (n = 53, 1SD) for the Cubulco, Pachajob and Agua Caliente granitoids, respectively.
Figure 6. Zircon trace element data for metamorphosed granitoids from the Chuacús high-pressure suite. (a) Th vs. U (μg/g); dashed lines indicate Th/U values of 0.1, 0.5 and 1. (b) Ti vs. Hf (μg/g) (c) (Eu/Eu*)/Y × 104 vs. ΔFMQ; ΔFMQ values are calculated as 3.998 × LOG(((Ce/U) × (U/Ti))0.5) + 2.284 (after Lu et al. Reference Lu, Loucks, Fiorentini, Mccuaig, Evans, Yang, Hou, Kirkland, Parra-Avila and Kobussen2016; Loucks et al. Reference Loucks, Fiorentini and Henríquez2020). (d) U/Yb vs. Nb/Yb tectonic discrimination diagram (Grimes et al. Reference Grimes, Wooden, Cheadle and John2015); MOR: mid-ocean ridge, OI: ocean-island.
Zircons from the Cubulco and Pachajob samples have chondrite-normalized Eu/Eu* average values (Eu/Eu* = EuN/(SmN × GdN)1/2) between 0.1 and 0.2, except for CH89 that show an average ratio of 0.4. By contrast, zircons from the Agua Caliente granitoids are characterized by a relatively high average Eu/Eu* value of 0.5. Similar trends are observed regarding the (Eu/Eu*)/Y × 104 hydration proxy of Lu et al. (Reference Lu, Loucks, Fiorentini, Mccuaig, Evans, Yang, Hou, Kirkland, Parra-Avila and Kobussen2016), with Agua Caliente and CH89 granitoids showing the highest data density with relatively high (>1) values (Fig. 6c). On the other hand, according to the relative oxygen fugacity (ΔFMQ) values, calculated using the method of Loucks et al. (Reference Loucks, Fiorentini and Henríquez2020), there is a clear distinction between most of the Mesoproterozoic samples, with values mainly from −3 to 0, and the Triassic Agua Caliente granitoid that ranges from 1 to 5 (Fig. 6c). Again, granitoid CH89 is the exception, showing ΔFMQ values between 0 and 4.
In the U/Yb vs. Nb/Yb discrimination diagram of Grimes et al. (Reference Grimes, Wooden, Cheadle and John2015), most data plot in the continental crust field, but a considerable number of zircons from the Cubulco (CH88 and CH89) and Agua Caliente samples fall within the ocean-island (OI)-type mantle array.
4.c. Sm-Nd and Lu-Hf isotope systematics
Sm-Nd and Lu-Hf isotope data, including TDM model ages, are presented in Table 2. Initial 143Nd/144Nd and 176Hf/177Hf ratios were recalculated at the protolith ages determined by U-Pb zircon dating (Maldonado et al. Reference Maldonado, Ortega-Gutiérrez and Ortíz-Joya2018b; this work). An age of 500 Ma was assumed for metapelite samples. The data show a positive correlation between εNdi and εHfi values, where granitoids conform well to the present-day Terrestrial Array (Vervoort et al. Reference Vervoort, Plank and Prytulak2011), while metapelite samples deviate by 6 to 7 εHf units above (Fig. 7a). Granitoids have initial isotopic compositions close to CHUR, with εNdi and εHfi values of −1.7–0.3 and −0.3–0.8, respectively.
Table 2. Sm-Nd and Lu-Hf data for metamorphic rocks from the Chuacús high-pressure suite
Initial (i) isotope ratios and ε values were recalculated according to U-Pb ages (Maldonado et al., Reference Maldonado, Weber, Ortega-Gutiérrez and Solari2018a) and to assumed ages of 500 Ma for pelitic schist samples. Depleted mantle (TDM) Sm-Nd model ages were calculated using present-day values of Liew and Hofmann (Reference Liew and Hofmann1988) and the λ147Sm value of Lugmair and Marti (Reference Lugmair and Marti1978). TDM Lu-Hf model ages were calculated using present-day values of Vervoort et al. (Reference Vervoort, Patchett, Albarède, Blichert-Toft, Rudnick and Downes2000) and the λ176Lu value of Scherer et al. (Reference Scherer, Münker and Mezger2001) and Söderlund et al. (Reference Söderlund, Patchett, Vervoort and Isachsen2004). εNd and εHf values were calculated using chondritic uniform reservoir (CHUR) values after Bouvier et al. (Reference Bouvier, Vervoort and Patchett2008).
Figure 7. Sm-Nd and Lu-Hf isotope data of whole-rock samples from the Chuacús high-pressure suite. (a) Initial εHf vs. εNd recalculated to estimated protolith ages shown in Table 2. εNd and εHf values are plotted with respect to the chondritic uniform reservoir (CHUR), using the data of Bouvier (Reference Bouvier, Vervoort and Patchett2008). The present-day Terrestrial Array, calculated as εHf = 1.55εNd + 1.21 (Vervoort et al. Reference Vervoort, Plank and Prytulak2011), is shown together with lines of constant deviation of Hf (ΔεHf) from this expression. The Seawater Array is as follows: εHf = 0.55εNd + 7.1 (Albarède et al. Reference Albarède, Simonetti, Vervoort, Blichert-Toft and Abouchami1998). The Metapelite line corresponds to a regression through the isotope compositions calculated at ages younger than the estimated maximum depositional ages. (b) 176Hf/177Hf vs. time diagram showing the isotopic evolution of the samples. The Depleted Mantle line is after Vervoort et al. (Reference Vervoort, Patchett, Albarède, Blichert-Toft, Rudnick and Downes2000). Dotted lines are deviations in +5 and −5 εHf increments from CHUR. (c) 143Nd/144Nd vs. time diagram showing the isotopic evolution of the samples. The Depleted Mantle line is after Liew & Hofmann (Reference Liew and Hofmann1988). Analogous to the Hf plot, dotted lines are deviations in +5 and −5 εNd increments from CHUR.
Figure 7b shows the Hf isotope ratios in a 176Hf/177Hf vs. time isotope evolution diagram, where samples display different evolution trends according to protolith ages. Granitoids from the Agua Caliente unit have initial Hf isotope ratios of 0.282644–0.282662 and the corresponding TDM Hf model ages range from 1.04 to 1.02 Ga. The Pachajob gneiss has an initial Hf isotope ratio of 0.282159 and a TDM Hf model age of 1.50 Ga. In contrast, granitoids from the Cubulco unit have initial ratios between 0.282074 and 0.282167, with relatively older TDM Hf model ages between 1.73 and 1.62 Ga. Metapelites yield a narrow range of present-day Hf compositions from 0.282464 to 0.282500 and their TDM Hf model ages are between 1.63–1.60 Ga (Palibatz schist) and 1.83–1.77 Ga (northern Chuacús metapelite). The Nd evolution of the samples (Fig. 7c) is quite similar to that of Hf. However, the metapelite samples have Nd isotope compositions slightly less radiogenic, decreasing up to 3ε units. Granitoid samples have initial Nd isotope ratios of 0.512281–0.512310 (Agua Caliente unit), 0.511297 (Pachajob gneiss) and 0.511217–0.511328 (Cubulco unit), with calculated TDM Nd model ages of 0.93–0.88, 1.40 and 1.68–1.58 Ga, respectively. Again, metapelite samples show more restricted present-day Nd compositions ranging from 0.511900 to 0.511935, with TDM Nd model ages between 1.75 and 1.54 Ga.
5. Discussion
5.a. Petrogenesis and implications of granitoid magmatism
A range of ages has previously been reported for the igneous protoliths of the Chuacús HP suite (Ratschbacher et al. Reference Ratschbacher, Franz, Min, Bachmann, Martens, Stanek, Stübner, Nelson, Herrmann, Weber, López-Martínez, Jonckheere, Sperner, Tichomirowa, Mcwilliams, Gordon, Meschede and Bock2009; Solari et al. Reference Solari, Tuena, Gutíerrez and Obregón2011; Martens et al. Reference Martens, Brueckner, Mattinson, Liou and Wooden2012; Maldonado et al. Reference Maldonado, Weber, Ortega-Gutiérrez and Solari2018a, Reference Maldonado, Ortega-Gutiérrez and Ortíz-Joya2018b, Reference Maldonado, Solari, Schaaf and Weber2023). At present, three granitoid-bearing units are clearly distinguished on the basis of age and geochemical characteristics: 1) the Cubulco unit with ca. 1100–1010 Ma granitoids, 2) the Pachajob gneiss of ca. 990 Ma and 3) the Agua Caliente unit that contains ca. 225 Ma granitoids. Although granitic rocks of Ordovician age are also recognized in the region (Solari et al. Reference Solari, Tuena, Gutíerrez and Obregón2011), they are outside the presently defined limits of the HP suite and are not addressed in this section.
5.a.1. Stenian magmatism
Stenian granitoids from the Cubulco unit are mesoperthite-rich metaluminous to peraluminous and alkalic to alkalic-calcic rocks that share all the geochemical features common to A-type (ferroan) granites (Maldonado et al. Reference Maldonado, Ortega-Gutiérrez and Ortíz-Joya2018b). They show high Fe/(Fe +Mg) and K2O/Na2O ratios and high incompatible element contents, including Y, rare-earth elements (REE) and HFSE, which are typical for A-type granites (Collins et al. Reference Collins, Beams, White and Chappell1982; Whalen et al. Reference Whalen, Currie and Chappell1987; Bonin, Reference Bonin2007; Frost & Frost, Reference Frost and Frost2011). Their 10,000 × Ga/Al ratios vary from 2.8 to 3.3, within the global range of A-type granites reported by Whalen et al. (Reference Whalen, Currie and Chappell1987). Following the subdivision of Eby (Reference Eby1992), the Cubulco granitoids show an A2-type character (Y/Nb = 2.5–3.6), indicative of magma derived from a pre-existing continental crust. Trace element compositions of zircon can be used to evaluate the hydration and oxidation state as well as the tectono-magmatic source of a magma (Grimes et al. Reference Grimes, Wooden, Cheadle and John2015; Lu et al. Reference Lu, Loucks, Fiorentini, Mccuaig, Evans, Yang, Hou, Kirkland, Parra-Avila and Kobussen2016; Loucks et al. Reference Loucks, Fiorentini and Henríquez2020). Zircon trace element data for the Cubulco granitoids (Fig. 6) suggest reduced and variably hydrous crystallization conditions for the precursor magma and agree with a source in the continental crust with potential contributions from the mantle (e.g. CH88). This is true for all samples except for CH89 (ca. 1013 Ma), which suggest hydrous and oxidized conditions as well as influence from OI-type mantle material. In addition, the Ti-in-zircon thermometry suggest that the Cubulco granitoids crystallized at relatively high magmatic temperatures of 848 ± 56 °C. However, considering the ca. 100 m.y. spread in ages, this unit probably includes two granitoid groups (i.e. of ca. 1100 and 1030–1010 Ma), although no obvious petrographic or isotopic difference is observed between them.
The Cubulco unit displays a bimodal isotope distribution, where initial Nd and Hf isotope compositions of granitoids (εNdi = −1.7–0.3, εHfi = −0.3–0.8) are up to 10 ε units lower than those of associated eclogites (Fig. 8a) (Maldonado et al. Reference Maldonado, Solari, Schaaf and Weber2023). These data indicate that granitoids could not have been produced by differentiation of the eclogite precursor magma, implying the existence of two distinctly different magma sources. TDM model ages of the Cubulco granitoids (ca. 1.7–1.6 Ga) are significantly older (ca. 500–600 m.y.) than their crystallization ages, suggesting derivation of magma predominantly from a pre-existing less siliceous crustal source. Recycling of an older crust is also supported by inherited zircons with ages between ca. 1633 and 1235 Ma (Maldonado et al. Reference Maldonado, Ortega-Gutiérrez and Ortíz-Joya2018b). However, derivation of the precursor magmas from mafic crust alone seems unlikely, as the heat required to partially melt such a protolith would most certainly be associated with mantle upwelling (i.e. asthenospheric input). Considering the occurrence of coeval (ca. 1100–1030 Ma) metabasites (eclogites) (Maldonado et al. Reference Maldonado, Solari, Schaaf and Weber2023), the potential contribution from isotopically juvenile magmas cannot be dismissed. It is worth noting that alkalic to alkalic-calcic A-type granitoid suites, with metaluminous or even peraluminous components, may be derived from differentiation of tholeiitic basalt magmas with variable amount of crustal contribution (Frost & Frost, Reference Frost and Frost2011). Therefore, mixing between magma derived from evolved crust and mantle-derived melts could have played an important role in generating the Cubulco granitoids. Although the negative Eu anomalies (Eu/Eu*=0.5–0.7) of these granitoids, together with their apparent negative correlations of Eu/Eu* vs. SiO2 and HFSE (Maldonado et al. Reference Maldonado, Ortega-Gutiérrez and Ortíz-Joya2018b) might indicate feldspar fractionation, additional work is needed to clarify the influence of fractional crystallization on deriving the granitic magmas. It is clear from the associated tholeiitic metabasites that this igneous suite might have involved asthenospheric melts produced either in a post-orogenic, intracontinental or back-arc setting (Collins et al. Reference Collins, Huang, Bowden and Kemp2020).
Figure 8. 143Nd/144Nd vs. time plots showing the isotopic evolution of whole rocks from the Chuacús high-pressure suite together with reference data used for comparison, as discussed in the text. The parameters and nomenclature are the same as in Figure 7. Whole-rock reference data is from (1) Maldonado et al. (Reference Maldonado, Solari, Schaaf and Weber2023); (2) Lopez et al. (Reference Lopez, Cameron and Jones2001); (3) Patchett and Ruiz (Reference Patchett and Ruiz1987), Ruiz et al. (Reference Ruiz, Patchett and Ortega-Gutiérrez1988), Weber and Köhler (Reference Weber and Köhler1999), Weber et al. (Reference Weber, Scherer, Schulze, Valencia, Montecinos, Mezger and Ruiz2010); (4) Weber et al. (Reference Weber, González-Guzmán, Manjarrez-Juárez, Cisneros De León, Martens, Solari, Hecht and Valencia2018); (5) Restrepo-Pace et al. (Reference Restrepo-Pace, Ruiz, Gehrels and Cosca1997), Ibanez-Mejia (Reference Ibanez-Mejia, Pullen, Arenstein, Gehrels, Valley, Ducea, Mora, Pecha and Ruiz2015); (6) Spikings et al. (Reference Spikings, Reitsma, Boekhout, Mišković, Ulianov, Chiaradia, Gerdes and Schaltegger2016); (7) Cochrane et al. (Reference Cochrane, Spikings, Gerdes, Ulianov, Mora, Villagómez, Putlitz and Chiaradia2014); (8) Solari et al. (Reference Solari, Tuena, Gutíerrez and Obregón2011); (9) Tazzo-Rangel et al. (Reference Tazzo-Rangel, Weber, González-Guzmán, Valencia, Frei, Schaaf and Solari2019); (10) Ortega-Obregon et al. (Reference Ortega-Obregón, Murphy and Keppie2010); (11) Murphy et al. (Reference Murphy, Keppie, Braid and Nance2005); (12) González-Guzmán et al. (Reference González-Guzmán, Weber, Manjarrez-Juárez, Cisneros De León, Hecht and Herguera-García2016); (13) Weber et al. (Reference Weber, Scherer, Martens and Mezger2012).
Nd and Hf isotope data from the Stenian A-type granitoids in the Chuacús HP suite reflect the existence of a basement with crustal residence ages of at least 1.7–1.6 Ga. The isotopic evolution trends of these rocks, in general, coincide with those of the eclogites from the El Chol unit (Maldonado et al. Reference Maldonado, Solari, Schaaf and Weber2023) (Fig. 8a). Even though the apparently Ectasian (ca. 1310 Ma) age of the El Chol mafic protoliths must still be confirmed, their isotopic similarity to the A-type Cubulco granitoids would indicate a genetic relationship between both units. Moreover, the ca. 1630 Ma zircon inheritance in the Cubulco granitoids (Maldonado et al. Reference Maldonado, Ortega-Gutiérrez and Ortíz-Joya2018a) suggests the recycling of late Palaeoproterozoic crust that might be similar to the Calymmian basement recently discovered in the nearby Chiapas Massif (Valencia-Morales et al. Reference Valencia-Morales, Weber, Tazzo-Rangel, González-Guzmán, Frei, Quintana-Delgado and Rivera-Moreno2022). The Nd evolution is also in the range of the late Mesoproterozoic basement of Mexico (e.g. Oaxaquia; Fig. 8a), and some notable similarities also exist between the Cubulco granitoids and contemporaneous rocks from the cordilleran inliers of Colombia, particularly the Guapotón gneiss in the Garzón Massif (Ibanez-Mejia et al. Reference Ibanez-Mejia, Pullen, Arenstein, Gehrels, Valley, Ducea, Mora, Pecha and Ruiz2015). A review of potential correlations between the Cubulco unit and areas recording Stenian bimodal (LIP-related) magmatism across Amazonia, Baltica and Laurentia was recently presented in Maldonado et al. (Reference Maldonado, Solari, Schaaf and Weber2023). One important additional observation is that most of the Stenian A-type plutonism around Rodinia is associated with rift-hotspot activity within Laurentia (Condie et al. Reference Condie, Pisarevsky, Puetz, Roberts and Spencer2023). An exception to this is the Sunsás belt of Bolivia (Amazonia), were hybrid A-type granitoids were produced during post-collisional magmatism at ca. 1.1 Ga (Nedel et al. Reference Nedel, Fuck, Ruiz, Matos and Ferreira2020).
5.a.2. Tonian magmatism
The Pachajob gneiss, with protolith ages of ca. 990 Ma, consists of a high-silica, peraluminous and alkalic-calcic granitoid, interpreted by Maldonado et al. (Reference Maldonado, Ortega-Gutiérrez and Ortíz-Joya2018b) as a crustal partial melt. These authors also reported a highly fractionated REE pattern with concave heavy REE profile as well as negative Ta, Nb, Sm and Ti anomalies, which probably indicate a source in a middle-lower crust with residual amphibole/clinopyroxene and rutile. Zircon trace element data presented in this work (Fig. 6) are consistent with a magma of crustal origin that crystallized under reduced and variably hydrous conditions (see discussion above).
Just as for the Cubulco granitoids, the crystallization age of the Pachajob gneiss is significantly younger (ca. 400–500 m.y.) than the TDM model ages (Fig. 7). However, the Nd and Hf isotope evolution trends are less steep for the Pachajob gneiss and yield comparatively younger TDM model ages (1.5–1.4 Ga), indicating derivation from melting of rejuvenated crust. Figure 8a shows that model ages for the Pachajob gneiss fall between those from the Cubulco unit (granitoids and eclogites). Accordingly, taking into account the protolith age and zircon inheritance (ca. 1200–1120 Ma) of the Pachajob gneiss (Maldonado et al. Reference Maldonado, Ortega-Gutiérrez and Ortíz-Joya2018b), we interpret that the magma was sourced from a crust similar in age and composition to the Cubulco unit. The Ti-in-zircon thermometer suggests a relatively high crystallization temperature of the magma of 848 ± 27 °C. Therefore, considering that mafic (tholeiitic) magmatism within the currently adjacent Cubulco unit probably spans the Stenian-Tonian boundary (Maldonado et al. Reference Maldonado, Solari, Schaaf and Weber2023), it is plausible that the associated heat transfer induced partial melting of the latest Mesoproterozoic middle-lower crust. Even if this interpretation is valid, whether the Pachajob and the youngest Cubulco (1030–1010 Ma) granitoids would represent a single long-lived episode of extensional magmatism or two separated episodes remains to be demonstrated.
Initial Nd ratios of the Pachajob gneiss are slightly less radiogenic but overall comparable with those of AMCG (anorthosite-mangerite-charnockite-granite) suite rocks from Oaxaquia and granitic orthogneiss from the Chiapas Massif (Weber & Köhler, Reference Weber and Köhler1999; Weber et al. Reference Weber, González-Guzmán, Manjarrez-Juárez, Cisneros De León, Martens, Solari, Hecht and Valencia2018) (Fig. 8a). An alternative correlation for the early Tonian anatexis recorded by the Pachajob gneiss is the late Mesoproterozoic (ca. 1.05–1.02 Ga) migmatization identified in both the Cordilleran inliers and the Putumayo Basin basement of Colombia (Cordani et al. Reference Cordani, Cardona, Jimenez, Liu and Nutman2005; Ibanez-Mejia et al. Reference Ibanez-Mejia, Ruiz, Valencia, Cardona, Gehrels and Mora2011; Ibanez-Mejia et al. Reference Ibanez-Mejia, Pullen, Arenstein, Gehrels, Valley, Ducea, Mora, Pecha and Ruiz2015), which has been interpreted as related to accretionary tectonics.
5.a.3. Late Triassic magmatism
Late Triassic megacrystic granitoids within the Agua Caliente unit are metaluminous to peraluminous and alkalic-calcic, showing enrichment in light REE and flat heavy REE profiles, negligible or absent Sr and Eu anomalies and relatively high HFSE concentrations (Solari et al. Reference Solari, Tuena, Gutíerrez and Obregón2011; Maldonado et al. Reference Maldonado, Ortega-Gutiérrez and Ortíz-Joya2018b). These features reflect negligible fractional crystallization of a magma that incorporate an enriched component. On the other hand, U/Yb vs. Nb/Yb covariation in zircon (Grimes et al. Reference Grimes, Wooden, Cheadle and John2015) (Fig. 6d) suggests a magma formed by mixing of continental crust and enriched mantle material. Coeval tholeiitic metabasites (eclogites) were interpreted by Maldonado et al. (Reference Maldonado, Solari, Schaaf and Weber2023) as produced from an enriched sub-lithospheric mantle during a pulse of intraplate continental magmatism. The initial isotope compositions of the Agua Caliente granitoids (εNdi = −1.1, −0.6, εHfi = 0, 0.6) are up to 4 ε units below the values of associated eclogite (Fig. 8b). As TDM model ages (ca. 1.0–0.9 Ga) for the granitoids are significantly older than the ages of crystallization (ca. 225 Ma), the magmas must have incorporated an important volume of older crustal material. This interpretation is supported by Stenian-Tonian (ca. 1050–980 Ma) zircon inheritance within these rocks (Maldonado et al. Reference Maldonado, Ortega-Gutiérrez and Ortíz-Joya2018b). Accordingly, an explanation that likely accounts for the origin of the Agua Caliente granitoids envisages a magma derived largely from older (late Mesoproterozoic) continental crust (e.g. Cubulco unit), with additional contributions from enriched mantle material. Thermal maturation and collapse of a thickened orogenic crust may result in extensive hybridization of partial melts derived from a heterogeneous lower crust and enriched mantle (Jacob et al. Reference Jacob, Moyen, Fiannacca, Laurent, Bachmann, Janoušek, Farina and Villaros2021). A post-collisional setting, rather than an intraplate one, would be more consistent with oxidized and relatively hydrous crystallization conditions, as suggested by zircon trace element compositions (Fig. 6c). Although magmatic temperatures for the Agua Caliente granitoids, estimated at 741 ± 60 °C, are lower than would be expected in a post-collisional setting (Sylvester, Reference Sylvester1998), the paucity of inherited zircon would indicate that melting temperatures were above zircon saturation and eventually sufficient to melt a fertile crust (e.g. Gerdes et al. Reference Gerdes, Wörner and Henk2000).
As discussed previously in Maldonado et al. (Reference Maldonado, Weber, Ortega-Gutiérrez and Solari2018a, Reference Maldonado, Solari, Schaaf and Weber2023), the Agua Caliente unit is mostly correlative with regions representing a western Pangea rift system during the Late Triassic in what is today western and northern South America. Figure 8b shows that granitoids from the Agua Caliente unit have initial Nd isotope ratios in the range of Nd compositions of silicic rocks from the Venezuelan and Peruvian Andes (Spikings et al. Reference Spikings, Reitsma, Boekhout, Mišković, Ulianov, Chiaradia, Gerdes and Schaltegger2016; Tazzo-Rangel et al. Reference Tazzo-Rangel, Weber, González-Guzmán, Valencia, Frei, Schaaf and Solari2019). However, the mafic components are considerably less radiogenic than metabasite and mafic volcanics of that region (Cochrane et al. Reference Cochrane, Spikings, Gerdes, Ulianov, Mora, Villagómez, Putlitz and Chiaradia2014). Whether the Agua Caliente unit included Triassic magmas sourced from a depleted mantle, either pristine or later modified by contamination, is still an unsolved subject that goes beyond the scope of this paper.
5.b. Palaeozoic and Mesozoic sedimentary record
The Chuacús HP suite contains abundant metasedimentary rocks, including pelitic schist, quartzite, marble and calc-silicate rocks. The youngest detrital zircon populations in the Palibatz schist (southern Sierra de Chuacús) occur at ca. 920 and 670 Ma (Solari et al. Reference Solari, Tuena, Gutíerrez and Obregón2011, this work), indicating a post-Cryogenian depositional age of its protolith. The minimum age of deposition is constrained by Lu-Hf ages of ca. 100 Ma, obtained from metamorphic garnet (Maldonado et al. Reference Maldonado, Weber, Ortega-Gutiérrez and Solari2018a). The isotopic compositions of the Palibatz schist deviate more than 4 εHf units above the Terrestrial Array (Fig. 7a), reflecting a zircon deficit that is typical of terrigenous clays dominated by continental sources (Albarède et al. Reference Albarède, Simonetti, Vervoort, Blichert-Toft and Abouchami1998; Vervoort et al. Reference Vervoort, Plank and Prytulak2011). Although Hf isotopic signatures in marine sediments are controlled by Lu/Hf fractionation during weathering, transport and diagenesis, the Nd composition is basically unaffected by these processes, reflecting the signature of the source regions (Vervoort et al. Reference Vervoort, Plank and Prytulak2011). Therefore, the Sm-Nd systematics can be used to trace the provenance of the Palibatz schist. TDM Nd model ages of 1.8 and 1.5 Ga express the integrated age of all crustal components in this unit. These ages are in the range of TDM Nd model ages of the Cubulco granitoids and the El Chol unit (Fig. 8c) and also coincide with those reported for the basement exposures of Oaxaquia and the Colombian Andes (Ruiz et al. Reference Ruiz, Patchett and Ortega-Gutiérrez1988); Weber & Köhler, Reference Weber and Köhler1999; Lopez et al. Reference Lopez, Cameron and Jones2001); Ibanez-Mejia et al. Reference Ibanez-Mejia, Pullen, Arenstein, Gehrels, Valley, Ducea, Mora, Pecha and Ruiz2015), suggesting that most of the detritus could have been derived from Mesoproterozoic crust. The Palibatz schist is characterized by major detrital zircon peaks at ca. 1.5, 1.2 and 1.0 Ga. Potential sources of these zircon components may be igneous and metamorphic rocks within Oaxaquia and the Chiapas Massif (Solari et al. Reference Solari, Keppie, Ortega-Gutiérrez, Cameron, Lopez and Hames2003; Weber et al. Reference Weber, Scherer, Schulze, Valencia, Montecinos, Mezger and Ruiz2010; Weber et al. Reference Weber, González-Guzmán, Manjarrez-Juárez, Cisneros De León, Martens, Solari, Hecht and Valencia2018; Valencia-Morales et al. Reference Valencia-Morales, Weber, Tazzo-Rangel, González-Guzmán, Frei, Quintana-Delgado and Rivera-Moreno2022), the Cordilleran-Putumayo basement (Cuadros et al. Reference Cuadros, Botelho, Ordóñez-carmona and Matteini2014; Ibanez-Mejia et al. 2015) and the Amazonian craton (Bettencourt et al. Reference Bettencourt, Tosdal, Leite and Payolla1999; Teixeira et al. Reference Teixeira, Geraldes, Matos, Ruiz, Saes and Vargas-Mattos2010). On the other hand, these age spectra are also characteristic of pre-Ordovician (meta)sedimentary sequences across the Maya block and surrounding areas in Mexico. For instance, early Palaeozoic rocks of the Acatlán and El Triunfo complexes of southern Mexico (Talavera-Mendoza et al. Reference Talavera-Mendoza, Ruiz, Gehrels, Meza-Figueroa, Vega-Granillo and Campa-Uranga2005; Weber et al. Reference Weber, Valencia, Schaaf, Pompa-Mera and Ruiz2008; Ramos-Arias & Keppie, Reference Ramos-Arias and Keppie2011; González-Guzmán et al. Reference González-Guzmán, Weber, Manjarrez-Juárez, Cisneros De León, Hecht and Herguera-García2016), the San Gabriel unit of central Guatemala (Solari et al. Reference Solari, Ortega-Gutiérrez, Elías-Herrera, Schaaf, Norman, De León, Ortega-Obregón, Chiquín and Ical2009) and the Baldy unit of Belize (Martens et al. Reference Martens, Weber and Valencia2010) contain distinctive Stenian (1.2–1.0 Ga) and Calymmian (ca. 1.5 Ga) zircon populations. Given the conspicuous absence of early Palaeozoic zircon in the Palibatz schist and the overall similarity to pre-Ordovician sequences in the region, we interpret that the protolith of this unit was deposited between the Ediacaran and the early Palaeozoic. This interpretation is in agreement with the occurrence of HP calc-silicate rocks with protolith ages constrained between ca. 1020 and 420 Ma (Maldonado et al. Reference Maldonado, Solari, Schaaf and Weber2023). Figure 8c shows that the Nd evolution trends of the Palibatz samples are in the range of those of the Zacango (Acatlán Complex), Jocote (Triunfo Complex) and Tiñu units of southern Mexico (Murphy et al. Reference Murphy, Keppie, Braid and Nance2005; Ortega-Obregón et al., Reference Ortega-Obregón, Murphy and Keppie2010; González-Guzmán et al. Reference González-Guzmán, Weber, Manjarrez-Juárez, Cisneros De León, Hecht and Herguera-García2016), whereas they clearly diverge from the Baldy unit (Weber et al. Reference Weber, Scherer, Martens and Mezger2012). Considering lithology, U-Pb ages and Sm-Nd isotopes, we note striking similarities with both the Jocote (Ediacaran) and Tiñu (Early Ordovician) units.
In addition to the late Neoproterozoic–early Palaeozoic sedimentary sequence, U-Pb ages of detrital zircon from different areas within the Chuacús HP suite suggest the existence of late Palaeozoic and post-Triassic strata (Ratschbacher et al. Reference Ratschbacher, Franz, Min, Bachmann, Martens, Stanek, Stübner, Nelson, Herrmann, Weber, López-Martínez, Jonckheere, Sperner, Tichomirowa, Mcwilliams, Gordon, Meschede and Bock2009; Solari et al. Reference Solari, Ortega-Gutiérrez, Elías-Herrera, Schaaf, Norman, De León, Ortega-Obregón, Chiquín and Ical2009; Solari et al. Reference Solari, Tuena, Gutíerrez and Obregón2011; Martens et al. Reference Martens, Brueckner, Mattinson, Liou and Wooden2012). Evidence for late Palaeozoic sedimentation comes from a single sample from northern Sierra de Chuacús, containing early Palaeozoic (480–402 Ma) detrital zircon (Solari et al. Reference Solari, Ortega-Gutiérrez, Elías-Herrera, Schaaf, Norman, De León, Ortega-Obregón, Chiquín and Ical2009). Unfortunately, additional evidence on the precise timing of this sedimentation period is currently lacking. In the Maya block, and several other areas of southern and eastern Mexico, early Palaeozoic rocks are overlain by clastic Carboniferous–Permian sequences (e.g. Santa Rosa Group) that typically contain Early Ordovician–Silurian detrital zircon (Weber et al. Reference Weber, Valencia, Schaaf and Ortega-Gutiérrez2009; Martens et al. Reference Martens, Weber and Valencia2010; Guerrero-Moreno et al. Reference Guerrero-Moreno, Solari, Ortega-Flores, Maldonado and Ortega-Obregón2023). Interestingly, our samples from northern Sierra de Chuacús (CH24, CH35), which belong to the structurally lower levels where HP features are visible, do not provide further evidence for this probable late Palaeozoic sequence. Both samples lack zircon populations spanning Ordovician to Silurian periods but have major components of Calymmian–Ectasian (1.5–1.2 Ga) zircon (Figs. 5c, d). Although some zircons yield early Palaeozoic or even younger (slightly discordant) ages, the evidence is not conclusive, and the rocks are ultimately more comparable to the Palibatz schist.
Post-Triassic sedimentation is inferred from eclogitic paragneisses showing a detrital zircon population spanning 280–220 Ma (Solari et al. Reference Solari, Tuena, Gutíerrez and Obregón2011; Martens et al. Reference Martens, Brueckner, Mattinson, Liou and Wooden2012). Based on their mineralogy which includes quartz, white mica, omphacite, garnet and rutile, we suggest that these rocks were probably derived from mixed quartzose and mafic volcanic sediments. Maldonado et al. (Reference Maldonado, Solari, Schaaf and Weber2023) reported Middle Jurassic (170–160 Ma) eclogite protoliths that likely formed from mafic volcaniclastic deposits with E-MORB affinity. We interpret that deposition of mixed sediments might have been simultaneous and closely related to Middle Jurassic E-MORB-like magmatism, in response to continental rift basin development around the proto-Gulf of Mexico. This record may potentially be correlated with several Middle Jurassic volcaniclastic sequences (mostly acid to intermediate) exposed from northern Mexico to Chiapas (Godínez-Urban et al. Reference Godínez-Urban, Lawton, Molina Garza, Iriondo, Weber and López-Martínez2011; Rubio-Cisneros & Lawton, Reference Rubio-Cisneros and Lawton2011), presently grouped into the Nazas rift province (Busby & Centeno-García, Reference Busby and Centeno-garcía2022).
6. Concluding remarks
Three periods of granitic magmatism at ca. 1100–1010, 990 and 225 Ma are recognized in the Chuacús HP suite. Stenian A-type granitoids within the bimodal Cubulco unit formed through mixing of magmas derived from late Palaeoproterozoic crust and mantle-derived melts produced either in a post-orogenic, intracontinental or back-arc setting within assembling Rodinia. Whether the Cubulco granitoids represent a protracted and continuous period (ca. 100 m.y.), or two separate pulses (1100 and 1030–1010 Ma) of magmatism remains an open question. The precursor magma of Tonian granitoids (Pachajob gneiss) was generated by partial melting of rejuvenated late Mesoproterozoic middle-lower crust associated with extensional tectonics. Late Triassic granitoids of the bimodal Agua Caliente unit were probably formed by mixing between melts derived from late Mesoproterozoic crust and melts derived from an enriched mantle in a post-collisional setting that evolved into continental rifting. This extensional stage, related to the western Pangea breakup, would have led to considerable thinning of the Chuacús crust and its consolidation as a passive margin that eventually subducted in the Cretaceous.
Even though the Chuacús HP suite may include late Palaeozoic and Jurassic metasedimentary rocks, most of the protoliths were probably deposited between the Ediacaran and the early Palaeozoic. The most characteristic unit is the Palibatz schist, which consists mainly of metapelite formed from terrigenous clays sourced from Mesoproterozoic continental areas such as the Chuacús basement itself or the basement inliers of southern Mexico and the northern Andes. This unit may correlate with peri-Gondwanan, Ediacaran to Cambro-Ordovician sequences of southern Mexico. The metapelite sequence from the northern Sierra de Chuacús does not provide further evidence for younger sedimentation periods, but rather correlates with the Palibatz schist.
Supplementary material
The supplementary material for this article can be found at https://doi.org/10.1017/S0016756824000347
Acknowledgments
This work was supported by the PAPIIT-DGAPA-UNAM project IA102523 and a DGAPA-UNAM-postdoctoral fellowship, both granted to R. Maldonado. We want to acknowledge P. Schaaf and B. Weber for providing analytical support and for discussions about the isotopic data. We also thank S. Morán-Ical for helping in the fieldwork. C. Ortega-Obregón, C. Macías-Romo, S. Padilla-Ramírez, G. Fernández-Catá, L. Luna, G. Arrieta-García and G. Solís-Pichardo are thanked for their technical assistance during the analytical procedures. Åke Johansson, Chunjing Wei and an anonymous referee provided very constructive review of the manuscript.
Competing interests
The authors declare none
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